Jiande copper deposit in Zhejiang Province was found in the 1960, and it is located in the northeastern part of Qinzhou-Hangzhou suture belt between Yangtze and Cathaysia blocks. Research about ore-forming fluids on it is still lacking. This study made a systematic investigation of fluid inclusions in the Jiande copper deposit. Based on petrographic observations of ore-bearing quartz collected from the massive ores, there are three types of primary inclusions of Jiande deposit:two-phase liquid-rich (type Ⅰ), two-phase vapor-rich (type Ⅱ), and halite-bearing (type Ⅲ) fluid inclusions. Type Ⅰ inclusions occur widely in the Jiande deposit and show homogenization temperatures of 220~377℃ and salinities of 0.63~8.00 wt.%NaCl equivalent. Type Ⅱ and type Ⅲ inclusions primarily coexist in ore veins. Homogenization temperatures of type Ⅱ and type Ⅲ reveal peak temperatures at 296~334℃and 290~326℃, respectively, and their salinities at 1.22~2.00 wt.%NaCl and 31.87~38.16 wt.%NaCl, respectively. The results indicate that fluid boiling process took place, and metal precipitation was probably induced by extensive fluid boiling events during the ore stage. Raman analysis of fluid inclusions indicates that, in the gaseous phase, water is dominant with small amount of CO2, CH4, and N2. Our study suggests that the Jiangde copper deposit is a Yanshanian Skarn deposit rather than a Hycernian Sedex Cu deposit.

The Huangshan gold deposit is hosted in the ductile shear zone of the metamorphosed Precambrian Chencai Group in the Jiangshan-Shaoxing fault zone between the Yangtze and the Cathaysia blocks. The mineralization can be divided into three stages: pre-ore stage barren quartz-sericite veins, ore stage quartz-pyrite veins, and post-ore stage calcite-quartz veins. A combination of fluid inclusion microthermometry and Raman spectroscopy analysis reveals three types of fluid inclusions: H2O-CO2-NaCl (type I), CO2-rich aqueous (type II), and aqueous fluid inclusions (type III). Primary fluid inclusions in the pre-ore stage quartz veins are mainly type I with low salinities (≤6 wt.% NaCl equivalents) that homogenized to liquid at moderate temperatures (298 to 371°C). Primary fluid inclusions in the ore stage quartz veins contain the following: type I fluid inclusions with variable CO2 volumetric ratios, which homogenized to liquid at moderate temperatures (287 to 376°C) and with moderate salinity (2.0 to 7.7 wt.% NaCl equivalents), type II (CO2 rich) inclusions of low salinity (1.6 to 4.8 wt.% NaCl equivalents), and type III fluid inclusions of low-moderate salinity (4.7 to 9.5 wt.% NaCl equivalents). In particular, some type II and III inclusions occur in the same isolated cluster or fracture, where type II inclusions homogenized into the CO2 phase (263 to 304°C) and type III inclusions into the aqueous phase (226 to 305°C) at almost the same temperature. This occurrence indicates that fluid immiscibility took place during ore-forming processes. Aqueous secondary fluid inclusions in the trans-granular fracture of quartz grains and primary inclusions in the post-ore stage calcite display low homogenization temperature (135 to 227°C and low to moderate salinity (0.2 to 5.5 wt.% NaCl equivalents). Trapping pressures of the immiscible fluid inclusion assemblages from ore stage veins are between 87 and 162MPa, indicating the gold-bearing quartz veins were precipitated deeper than 3.2km. These pressures are too high and exclude the previously proposed epithermal model for this deposit. Raman spectroscopy shows that volatile compositions in the CO2-bearing inclusions are primarily CO2 with minor N2. The oxygen and hydrogen isotope compositions (δD=−56‰ to −67‰; δ18O=3.3‰ to 4.4‰) imply a likely metamorphic origin of the ore stage fluids. Sulfur (+4.1‰ to +5.4‰) and lead (206Pb/204Pb: 17.606 to 17.704; 207Pb/204Pb: 15.490 to 15.536; 208Pb/204Pb: 37.701 to 38.083) isotopes of the ore minerals show similar signatures to the host rocks of the Chencai Group. These data strongly indicate that the Huangshan gold deposit is an orogenic-type deposit. Combined with previously published geochronology data and the geological setting, we stress the existence of a Caledonian orogenic gold belt along the Jiangshan-Shaoxing fault zone and thus suggest an extensive target area for further gold exploration along the Jiangshan-Shaoxing fault zone.

The Makeng iron deposit is located in the Yong'an-Meizhou depression belt in Fujian Province, eastern China. Both skarn alteration and iron mineralization are mainly hosted within middle Carboniferous lower Permian limestone. Five paragenetic stages of skarn formation and ore deposition have been recognized: Stage 1, early skarn (andradite-grossular assemblage); Stage 2, magnetite mineralization (diopside-magnetite assemblage); Stage 3, late skarn (amphibole-chlorite-epidote-johannsenite-heden bergite-magnetite assemblage); Stage 4, sulfide mineralization (quartz-calcite-fluorite-chlorite-pyritegalena-sphalerite assemblage); and Stage 5, carbonate (quartz -calcite assemblage). Fluid inclusion studies were carried out on inclusions in diopside from Stage 2 and in quartz, calcite, and fluorite from Stage 4.Halite-bearing (Type 1) and coexisting two-phase vapor-rich aqueous (Type 3) inclusions in the magnetite stage display homogenization temperatures of 448-564 degrees C and 501-594 degrees C, respectively. Salinities range from 26.5 to 48.4 and 2.4 to 6.9 wt% NaCI equivalent, respectively. Two-phase liquid-rich aqueous (Type 2b) inclusions in the sulfide stage yield homogenization temperatures and salinities of 182-343 degrees C and 1.9-20.1 wt% NaCI equivalent. These fluid inclusion data indicate that fluid boiling occurred during the magnetite stage and that fluid mixing took place during the sulfide stage. The former triggered the precipitation of magnetite, and the latter resulted in the deposition of Pb, Zn, and Fe sulfides. The fluids related to magnetite mineralization have delta O-18(fluid-vsmow) of 6.7-9.6 parts per thousand and ED of -96 to -128 parts per thousand, which are interpreted to indicate residual magmatic water from magma degassing. In contrast, the fluids related to the sulfide mineralization show delta O-18(fluid-vsmow) of 0.85 to 1.04%o and ED of -110 to -124 parts per thousand, indicating that they were generated by the mixing of magmatic water with meteoric water. Magnetite grains from Stage 2 exhi"bit oscillatory zoning with compositional variations in major elements (e.g., SiO2, Al2O3, CaO, MgO, and Mn0) from core to rim, which is interpreted as a self-organizing process rather than a dissolutionreprecipitation process. Magnetite from Stage 3 replaces or crosscuts early magnetite, suggesting that later hydrothermal fluid overprinted and caused dissolution and reprecipitation of Stage 2 magnetite. Trace element data (e.g., Ti, V, Ca, Al, and Mn) of magnetite from Stages 2 and 3 indicate a typical skarn origin. (C) 2016 Elsevier B.V. All rights reserved.

Makeng iron deposit is a large scale Fe-Mo-Pb-Zn polymentallic deposit in Fujian province hosted in the external contact zone of Juzhou-Dayang granites between the Jingshe Formation-Qixia Formation marbles and the Lindi Formation quartz sandstones. Mineralization stages can be classified into four stages: (1) anhydrous skarn stage (andradite-diopside); (2) hydrous skarn-magnetite (epdiote-chlorite-actinolite-hedenbergite);(3) sulfides stage (quartz-calcite-fluorite-sphalerite-galena);(4) carbonates stage (quartz-calcite). Petrographic and microthermometric studies of fluid inclusions in hedenbergite, fluorite, quartz and calcite of different mineralization stages show that the fluid inclusions related to magnetite mineralization are dominated by daughter mineral-bearing fluid inclusions, liquid-rich aqueous fluid inclusions, and minor vapor-rich fluid inclusions; fluid inclusions in sulfide mineralization stage mainly include liquid-rich aqueous fluid inclusions. Ore fluid in iron oxide stage evidence for boiling at the temperature range of 448 to 596℃, with salinities of 26.5 to 48.4 wt%NaCl equiv. for one end member fluid and 2.4 to 6.9 wt%NaCl equiv. for the other end member fluid. Whereas ore-forming fluid in sulfide stage exhibits a mixing trend, with the temperature and salinity of 182 to 343℃and 1.9 to 20.1 wt % NaCl equiv., respectively. Based on the fluid-inclusion data, early-stage magnetite mineralization fluids were originated mainly from magmatic water, and late-stage sulfide mineralization fluids were derived from mixtures of magmatic water and meteoric water. Because Fe mineralization was formed in the hydrous skarn stage and Pb-Zn mineralization was formed in the sulfide stage, the early-stage magnetite deposition may have resulted from fluid boiling and the late-stage sulfide deposition may have contributed to fluid mixing between magmatic water and meteoric water. Overall, the Makeng deposit is interpreted as a skarn type Fe-Mo-Pb-Zn polymentallic deposit related to intermediate-acid pluton based on skarn mineralogy and fluid inclusion characteristics.

The Cathaysia Block is the southeastern part of the South China Block in Southeast (SE) China, and it hosts voluminous late Mesozoic I-, S-, and A -type granitoids, as well as minor highly fractionated granites. We present here zircon U-Pb age data and Nd-Hf isotopic data for the Dayang and Juzhou granites, together with new petrological and geochemical analyses. The Dayang pluton consists of fine-grained two-mica monzonitic granites in which the plagioclases exhibit zoning and poikilitic textures. In contrast, the Juzhou pluton consists of medium-to coarse-grained biotite K-feldspar granites that lack zoning and poikilitic textures. The emplacement ages are 143 +/- 2.3 Ma for the Dayang pluton and 133 +/- 2.1 Ma for the Juzhou pluton according to zircon U-Pb isotope analyses. The Dayang and Juzhou granites are both metaluminous and belong to the shoshonitic series. The Dayang granite exhibits very flat REE patterns, showing the tetrad effect, and the spidergrams show striking negative Ba, Sr, Nb, and Ti anomalies and a positive Ta anomaly. In contrast, the Juzhou granite has sloping REE patterns, but like the Dayang granite it also has striking negative Ba, Sr, Nb, Ta, and Ti anomalies. Petrographic and geochemical evidence indicates that the Dayang granite is a highly fractionated I -type granite and that the Juzhou granite is a typical I -type granite. The tetrad effect in the Dayang granite can be interpreted in terms of melt -rock interactions at a late stage of magma evolution, whereas the main mechanism during the evolution of the Juzhou magma was fractionation of plagioclase, biotite, hornblende, apatite, zircon, and allanite. Nd-Hf isotope data suggest that the Dayang and Juzhou granites were both formed partial melting of Paleoproterozoic basement rock and juvenile material (underplating basalts or Mayuan Group amphibolites), with the Juzhou granite having a greater contribution from juvenile material than the Dayang granite. Our new data, together with existing data, suggest that the tectonic setting of the early Yanshanian (-143 Ma) highly fractionated I -type Dayang granite was a back-arc that formed in response to the westward subduction of the Paleo-Pacific Plate, and that the late Yanshanian (similar to 133 Ma) Juzhou granite formed in a continental arc setting in response to rollback of the Paleo-Pacific Plate toward the coastline. The Mo mineralization in the Makeng ore area was probably the result of the exsolution of Mo-bearing fluids from the Dayang granitic magmas due to extensive fractional crystallization. (C) 2016 Elsevier Ltd. All rights reserved.

The giant Dexing porphyry copper deposit is one of the largest porphyry copper deposits in South China. This paper presents new LA-ICP-MS zircon U–Pb dating, element and Sr–Nd–Hf isotopic data for the ore-related porphyries in the Dexing porphyry deposit. The Dexing ore-related porphyries were emplaced during the Middle Jurassic (ca. 170 Ma), and were characterized by high-Mg adakitic geochemical features, including high MgO and Sr contents and high Mg#, Sr/Y and LaN/YbN ratios, low Y and Yb contents, and lacking a negative Eu anomaly, which suggest that they were probably derived from the delaminated thickened lithosphere. A non-arc setting in the Middle Jurassic is indicated by the absence of arc rocks and the presence of rifting-related igneous rock associations in the interior of South China. The non-arc setting suggests that the copper-rich lithosphere in the Dexing area was enriched by an ancient subduction event prior to the Late Mesozoic. The regional geological history and the Neoproterozoic two-stage Nd–Hf isotope model ages imply that the ancient subduction event occurred in the Neoproterozoic in response to the Jiangnan Orogen between the Yangtze and Cathaysia blocks. Thus, we infer that the giant Dexing porphyry copper deposit was formed in the Middle Jurassic by remelting of the copper-rich Neoproterozoic subduction-modified lithosphere. Previous studies of the low-Mg ore-related porphyries in the adjacent Yinshan copper polymetallic deposit proposed a copper-rich juvenile crust as their magma source. In this study, the high Mg contents of the Dexing ore-related porphyries stress the significant contribution of the subduction-modified lithospheric mantle or a higher melting temperature.

The Pingshui Cu–Zn deposit is located in the Jiangshan–Shaoxing fault zone, which marks the Neoproterozoic suture zone between the Yangtze block and Cathaysia block in South China. It contains 0.45million tons of proven ore reserves with grades of 1.03wt.% Cu and 1.83wt.% Zn. This deposit is composed of stratiform, massive sulfide ore bodies, which contain more than 60vol.% sulfide minerals. These ore bodies are hosted in altered mafic and felsic rocks (spilites and keratophyres) of the bimodal volcanic suite that makes up the Neoproterozoic Pingshui Formation. Metallic minerals include pyrite, chalcopyrite, sphalerite, tennantite, tetrahedrite and magnetite, with minor galena. Gangue minerals are quartz, sericite, chlorite, calcite, gypsum, barite and jasper. Three distinct mineralogical zones are recognized in these massive sulfide ore bodies: a distal zone composed of sphalerite+pyrite+barite (zone I); an intermediate zone characterized by a pyrite+sphalerite+chalcopyrite assemblages (zone II); and a proximal zone containing chalcopyrite+pyrite+magnetite (zone III). A thin, layer of exhalative jaspilite overlies the sulfide ore bodies except in the proximal zone. The volcanic rocks of the Pingshui Formation are all highly altered spilites and keratophyres, but their trace element geochemistry suggests that they were generated by partial melting of the depleted mantle in an island arc setting. Homogenization temperatures of the primary fluid inclusions in quartz from massive sulfide ores are between 217 and 328°C, and their salinities range from 3.2 to 5.7wt.% NaCl equivalent. Raman spectroscopy of the fluid inclusions showed that water is the dominant component, with no other volatile components. Fluid inclusion data suggest that the ore-forming fluids were derived from circulating seawater. The δ34S values of pyrite from the massive sulfide ores range from −3.6‰ to +3.4‰, indicating that the sulfur was primarily leached from the arc volcanic rocks of the Pingshui Formation. Both pyrite from the massive sulfide ores and plagioclase from the spilites have similar lead isotope compositions, implying that the lead was also derived from the Pingshui Formation. The low lead contents of the massive sulfide ores and the geochemistry of their host rocks are similar to many VMS Cu–Zn deposits in Canada (e.g., Noranda) and thus can be classified as belonging to the bimodal-mafic subtype. The presence of magnetite and the absence of jaspilite and barite at the −505m level in the Pingshui deposit suggest that this level is most likely the central zone of the original lateral massive sulfide ore bodies. If this interpretation is correct, the deep part of the Pingshui Cu–Zn deposit may have significant exploration potential.

There are several gold deposits in the eastern section of the regional Jiang-Shao Fault between the Yangtze and Cathaysia Blocks in South China. Auriferous quartz veins in these deposits are strictly hosted in second-order NE-trending ductile shear zones. The ores generally contain low amounts of sulfide minerals (<5%), with pyrite as the most common sulfide mineral hosting native gold. Detailed fluid inclusion work and Rb-Sr dating were conducted on the auriferous quartz veins from the Pingshui and Huangshan deposits. H2O-CO2 inclusions (type I) and aqueous inclusions (type II) ubiquitously coexist in the main mineralization stage veins in the Huangshan and Pingshui deposits. Type I and II inclusions in the Huangshan deposit have similar homogenization temperatures at 214-282 degrees C, but different salinities with 1.2-6.0 and 2.7-8.7 wt.% NaCl equivalent, respectively. In the gold orebodies from the Pingshui deposit, type I and II inclusions also have similar homogenization temperatures ranging from 236 to 304 degrees C, but different salinities ranging from 1.2 to 6.4 and from 3.2 to 9.8 wt.% NaCl equivalent, respectively. Fluid inclusion observations and microthermometric results show that the ore fluids are low salinity and CO2-rich. Petrography and microthermometric results of fluid inclusions suggest that extensive fluid immiscibility occurred during the gold mineralization stage. Rb-Sr dating of quartz-hosted fluid inclusions (ca. 450 Ma) for the gold mineralization at Pingshui, combined with previous radiometric age data (ca. 397 Ma) of gold mineralization at Huangshan, suggest that the regional gold mineralization was formed in the Early Paleozoic. This study suggests that there is an Early Paleozoic orogenic gold belt in the eastern section of the Jiang Shao Fault, formed in response to the coeval northward underthrusting of the Cathaysia Block beneath the Yangtze Block during the Caledonian Orogeny in South China. (C) 2014 Elsevier Ltd. All rights reserved.

The Shapinggou porphyry Mo deposit, one of the largest Mo deposits in Asia, is located in the Dabie Orogen, Central China. Hydrothermal alteration and mineralization at Shapinggou can be divided into four stages, i.e., stage 1 ore-barren quartz veins with intense silicification, followed by stage 2 quartz-molybdenite veins associated with potassic alteration, stage 3 quartz-polymetallic sulfide veins related to phyllic alteration, and stage 4 ore-barren quartz±calcite±pyrite veins with weak propylitization. Hydrothermal quartz mainly contains three types of fluid inclusions, namely, two-phase liquid-rich (type I), two- or three-phase gas-rich CO2-bearing (type II) and halite-bearing (type III) inclusions. The last two types of fluid inclusions are absent in stages 1 and 4. Type I inclusions in the silicic zone (stage 1) display homogenization temperatures of 340 to 550°C, with salinities of 7.9–16.9wt.% NaCl equivalent. Type II and coexisting type III inclusions in the potassic zone (stage 2), which hosts the main Mo orebodies, have homogenization temperatures of 240–440°C and 240–450°C, with salinities of 34.1–50.9 and 0.1–7.4wt.% NaCl equivalent, respectively. Type II and coexisting type III inclusions in the phyllic zone (stage 3) display homogenization temperatures of 250–345°C and 220–315°C, with salinities of 0.2–6.5 and 32.9–39.3wt.% NaCl equivalent, respectively. Type I inclusions in the propylitization zone (stage 4) display homogenization temperatures of 170 to 330°C, with salinities lower than 6.5wt.% NaCl equivalent. The abundant CO2-rich and coexisting halite-bearing fluid inclusion assemblages in the potassic and phyllic zones highlight the significance of intensive fluid boiling of a NaCl–CO2–H2O system in deep environments (up to 2.3kbar) for giant porphyry Mo mineralization. Hydrogen and oxygen isotopic compositions indicate that ore-fluids were gradually evolved from magmatic to meteoric in origin. Sulfur and lead isotopes suggest that the ore-forming materials at Shapinggou are magmatic in origin. Re–Os dating of molybdenite gives a well-defined 187Re/187Os isochron with an age of 112.7±1.8Ma, suggesting a post-collisional setting.

Acta Geologica Sinica - English EditionVolume 88, Issue s2 p. 1073-1074 Meeting Abstracts Ore-forming fluids of two types of mineralization in Pingshui deposit, China Hui CHEN, Corresponding Author Hui CHEN State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaCorresponding author. E-mail: chenhui_nju@163.comSearch for more papers by this authorPei NI, Pei NI State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorGuoguang WANG, Guoguang WANG State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorYingfeng XU, Yingfeng XU State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorJunying DING, Junying DING State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorJunyi PAN, Junyi PAN State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorLi Lin, Li Lin State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this author Hui CHEN, Corresponding Author Hui CHEN State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaCorresponding author. E-mail: chenhui_nju@163.comSearch for more papers by this authorPei NI, Pei NI State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorGuoguang WANG, Guoguang WANG State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorYingfeng XU, Yingfeng XU State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorJunying DING, Junying DING State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorJunyi PAN, Junyi PAN State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this authorLi Lin, Li Lin State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093 ChinaSearch for more papers by this author First published: 29 December 2014 https://doi.org/10.1111/1755-6724.12379_6Read the full textAboutPDF ToolsRequest permissionExport citationAdd to favoritesTrack citation ShareShare Give accessShare full text accessShare full-text accessPlease review our Terms and Conditions of Use and check box below to share full-text version of article.I have read and accept the Wiley Online Library Terms and Conditions of UseShareable LinkUse the link below to share a full-text version of this article with your friends and colleagues. Learn more.Copy URL Share a linkShare onFacebookTwitterLinkedInRedditWechat No abstract is available for this article. Volume88, Issues2Special Issue: Meeting Abstracts: The 14th Quadrennial International Association on the Genesis of Ore Deposits Symposium. August 19–22, 2014, Kunming, ChinaDecember 2014Pages 1073-1074 RelatedInformation

The Jinshan gold deposit is located in the Neoproterozoic Jiangnan orogen between the Yangtze and Cathaysia blocks. Gold-bearing disseminated ores are associated with the earlier stage of NWW-trending ductile zone, and auriferous quartz vein-type ores show an intimate relationship with the later stage of NE-trending brittle-ductile zones. Fluid-inclusion studies were conducted on the quartz veins. Three types of fluid inclusions can be identified: H2O-CO2 inclusions (type I), CO2-rich inclusions (type II), and aqueous inclusions (type III). The pre-ore stage, quartz-pyrite veins primarily contain type I inclusions with constant CO2 bubble volumetric proportions. The main gold mineralization-stage veins have all three types of inclusions with variable gas-phase ratios and CO2 contents. The post-ore stage carbonate +/- chlorite veinlets only contain type III inclusions. Type I inclusions in the pre-ore stage display homogenization temperatures (Th) of 285-340 degrees C, with salinities of 1.4-6.1wt.% NaCl equivalent. In the main gold mineralization stage, type II and III inclusions show similar Th at 208-277 degrees C, but contrasting salinity values with 0.6-3.6 and 3.5-8.9wt.% NaCl equivalent, and type I inclusions show variable CO2-phase proportions and have Th of 241-292 degrees C and salinities of 1.0-7.0wt.% NaCl equivalent. In the post-ore stage, type III inclusions yield Th of 109-201 degrees C and salinities of 1.1-6.4wt.% NaCl equivalent. Petrological observations and microthermometric results show that fluid immiscibility primarily occurred during the gold mineralization stages. The oxygen and hydrogen isotope compositions ((18) O=+6.9 parts per thousand to +11.2 parts per thousand, D=-71 parts per thousand to -46 parts per thousand) of inclusion water in quartz grains imply that ore fluids were principally metamorphic in origin. The sulfur and lead values of sulfide from the ores are analogous to those from the basement strata, suggesting a predominantly crustal source of the ore sulfides. The Jinshan deposit is a typical orogenic gold deposit.

The meteorologic effects on soil radon is dealt with. The observations during a year at fixed locations show a clear pattern of seasonal variations of soil radon which is grossly lower during spring and summer, lowest in summer, and higher during autumn and winter, highest in winter. A fall of rain or show usually brings about a steep rise of soil radon concentration. At 0 degrees C or so, especially below 0 degrees C, radon values des cend greatly. Besides seasonal variations, soil radon concentration also has, diurnal changes, with a pattern. of lower values at noon and higher values in the early morning and in the evening. From the vertical profile, an optimum death for the measurement, which is 65-75 an, is recognized, where the radon value is maximal and diurnal variations are minimal. At last, measures are put forward to reduce or remove meteorologic effects on soil radon application.